Earth Planets Space, 64, 843–858, 2012
26 December 2004 tsunami deposits left in areas of various tsunami runup
in coastal zone of Thailand
Witold Szczuci´nski1, Grzegorz Rachlewicz2, Niran Chaimanee3, Darunee Saisuttichai4, Thawatchai Tepsuwan4, and Stanisław Lorenc1
1Institute of Geology, Adam Mickiewicz University in Pozna´n, Mak´ow Polnych 16, 61-606 Pozna´n, Poland 2Institute of Geoecology and Geoinformation, Adam Mickiewicz University in Pozna´n, Dzi
egielowa 27, 61-680 Pozna´n, Poland 3Coordinating Committee for Geoscience Programmes in East and Southeast Asia, Bangkok 10120, Thailand
4Department of Mineral Resources, Bangkok 10400, Thailand
(Received December 13, 2010; Revised March 4, 2012; Accepted July 19, 2012; Online published October 24, 2012)
The tsunami deposits left by the 26 December 2004 tsunami in the coastal zone of Thailand were studied within two months of the event and before any significant postdepositional changes could occur. The sediment structure and texture (grain size), as well as its thickness and spatial distribution, were documented for the tsunami deposits in 12 shore-perpendicular transects from areas of various tsunami runup and wave heights. The tsunami deposits were as thick as 0.4 m and were located as far as 1.5 km inland. They were composed mostly of poorly sorted sand and often consisted of one to four normally graded, massive or laminated layers. The deposits generally became finer in the landward direction; however, landward thinning trend of the deposits is not clear, and the maximum accumulation often is not located close to the shoreline but rather is further inland. In comparable coastal environments with similar available sediment sources the tsunami size (represented as the tsunami runup height) is reflected in the resulting deposits. Larger tsunamis are associated with deposits that are thicker, have a maximum accumulation located farther inland, include a finer sediment fraction (likely from deeper offshore areas) and frequently are composed of normally graded layers.
Key words: Tsunami deposits, 2004 Indian Ocean tsunami, tsunami runup, grain size, sedimentation, event
deposits, Thailand, Andaman Sea.
1.
Introduction
Tsunami waves often leave a fingerprint in a coastal zone in the form of sedimentary event deposits (Shiki et al., 2008; Bourgeois, 2009). During the last 15 years, much effort has been devoted to documenting the various recent tsunami deposits (Nishimura and Miyaji, 1995; Sato et al., 1995; Shi et al., 1995; Dawson et al., 1996; Minoura et al., 1997; Bourgeois et al., 1999; Gelfenbaum and Jaffe, 2003; Nanayama and Shigeno, 2006; Higman and Bourgeois, 2008; Goto et al., 2011; Moore et al., 2011). The major-ity of these works focused on documentation of the 2004 Indian Ocean Tsunami (IOT) depositional effects along the coasts of Sumatra (Moore et al., 2006; Razzhigaeva et al., 2006; Richmond et al., 2006; Paris et al., 2007, 2009), Thailand (Hori et al., 2007; Kelletat et al., 2007; Choowong
et al., 2008a, b; Matsumoto et al., 2008; Sawai et al., 2009;
Fujino et al., 2010; Naruse et al., 2010), Sri Lanka (Morton
et al., 2008), India (Bahlburg and Weiss, 2007; Srinivasalu et al., 2007) and Maldives (Kench et al., 2006).
There are two main reasons supporting the need for those studies. The first is to provide good diagnostic criteria to help identify paleotsunami deposits, which are necessary to improve the tsunami hazard assessment for a given coast
Copyright c The Society of Geomagnetism and Earth, Planetary and Space Sci-ences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sci-ences; TERRAPUB.
doi:10.5047/eps.2012.07.007
(e.g. Clague et al., 2000; Nanayama et al., 2007; Jankaew
et al., 2008). The explicit identification of paleotsunami
deposits is often difficult mainly because the tsunami de-posits may be represented by various sediment types and may be similar to other deposits, such as storm deposits (Morton et al., 2007; Switzer and Jones, 2008). Until now, there has been no simple universal diagnostic set of criteria that can be applied to analyse tsunami deposits with cer-tainty (Dawson and Shi, 2000; Goff et al., 2001; Scheffers and Kelletat, 2003; Shiki et al., 2008; Bourgeois, 2009; Chagu´e-Goff, 2010; Peters and Jaffe, 2010; Chagu´e-Goff et
al., 2011; Goff et al., 2012). The second reason to study the
recent tsunami deposits is to potentially gain insight into the processes and forces that exist during the tsunami inunda-tion. For instance, the studies of the tsunami deposits may be used to assess the water flow velocity and the depth of tsunami inundations. These studies can also identify how the tsunami affected the coastal geomorphology (Jaffe and Gelfenbaum, 2007; Smith et al., 2007; Paris et al., 2009). They are also necessary for the validation of tsunami sedi-ment transport models.
The tsunami deposits were documented by several re-search teams in the field within a few months after the IOT in parts of the Andaman Sea coastal zone of Thailand. The published results include works focused on the overall ge-ological impacts of the tsunami (Szczuci´nski et al., 2006; Choowong et al., 2007; Kelletat et al., 2007; Umitsu et
al., 2007), on the detailed analyses of sedimentary prop-843
erties of sandy deposits (Hori et al., 2007; Choowong et
al., 2008a, b; Fujino et al., 2008, 2010; Goto et al., 2008;
Matsumoto et al., 2008; Alam, 2010; Naruse et al., 2010) and on the boulder deposits (Goto et al., 2007; Yawsangratt
et al., 2009). Also studied were specific aspects such as
the micropaleontological features of the deposits (Hawkes
et al., 2007; Kokoci´nski et al., 2009; Sawai et al., 2009;
Yawsangratt et al., 2012), their geochemistry (Szczuci´nski
et al., 2005; Boszke et al., 2006; Kozak et al., 2008;
Zioła-Frankowska et al., 2009), their physical properties (Bishop
et al., 2005) and their mineralogy (Jagodzi´nski et al., 2009).
The IOT deposits were also presented in papers focused on paleotsunami deposits (Jankaew et al., 2008, 2011; Fujino
et al., 2009; Brill et al., 2011; Yawsangratt et al., 2012).
The aforementioned works revealed that the IOT deposits varied considerably regarding extent, thickness, grain size (mud to boulders), internal structures, composition and preservation potential. The deposits usually formed exten-sive sand sheets with a thickness ranging from a few cm to several tens of cm. They were commonly layered and normally graded, with evidence of both onshore and back-wash flows, and some components suggested origins from marine, brackish and terrestrial environments. While many works were published, the detailed sedimentological data have not yet been reported from the present study areas, par-ticularly the Patong Bay area and Kho Khao Island. Most of the previous studies are limited in the number of observa-tions (usually one or two transects or trenches). Further-more, the studies made no attempts to compare deposits left in areas of relatively similar topography and potential source sediments that experienced varied height of tsunami runup. Several studies were also conducted one or more years after a tsunami. However, they are not discussed here because they have not assessed the post-depositional changes that were found to be important in the case of the onshore tsunami deposits in Thailand (Szczuci´nski et al., 2006, 2007; Goto et al., 2008, 2012; Jankaew et al., 2008; Szczuci´nski, 2012), as well as in other parts of the Indian Ocean basin (Nichol and Kench, 2008).
This paper has four objectives:
- to provide a new documentation of the recent (i.e., not altered by post-depositional processes) onshore tsunami de-posits (spatial extent, thickness, sediment structure and tex-ture) from areas flooded by the 2004 IOT that experienced various runup heights,
- to interpret the possible tsunami-related sedimentation processes,
- to examine if variations in the tsunami runup heights are reflected in the tsunami deposit properties
- and to compare the new data with the existing common set of diagnostic features for tsunami deposits.
2.
Study Area and 2004 IOT
This study was conducted in the coastal zone of western Thailand (Phang Nga province and Phuket Island), which faces the Andaman Sea (Fig. 1). The studied sites represent either the rocky shorelines with small pocket beaches and narrow coastal plains (on Phuket Island: Tri Trang, Patong) or the long sandy beaches that are flanked by coastal plains as wide as 3 km (in Phang Nga province: Bang Sak, Bang
Mor, Kho Khao Island). The coastal plain is undulated be-cause of its formation processes (beach ridges and swales) as well as human activity (tin mining). The region is char-acterised by a warm climate with approximately 3000 mm of precipitation per year that primarily falls during the rainy season (May to September). The studied sites were investi-gated shortly after the IOT event, during the dry period, so no rainfall altered the freshly deposited tsunami sediments. On the 26th of December 2004, at 00:58:53 universal time, an earthquake of surface wave magnitude (Ms) 9.0
occurred off the west coast of northern Sumatra (Fig. 1(A)) (Lay et al., 2005) and generated tsunami waves that reached the coast of Thailand at Phuket Island approximately 100 minutes after the earthquake. The tsunami wave arrived during high tide with leading depression wave (Kawata et
al., 2005; Tsuji et al., 2006). Most of the eyewitness
re-ports documented two major waves, with a period of ap-proximately 40 minutes, inundating the coastal zone; sev-eral smaller waves were also documented. Altogether, up to 7 waves were reported by eyewitnesses (M˚ard Karlsson
et al., 2009). Some of the witnesses reported a smaller
wave arriving a few minutes before the main wave (M˚ard Karlsson et al., 2009). Alternatively, some witnesses re-ported several waves inundating the land in periods of a few minutes without intervening water withdrawals (Choowong
et al., 2008b). In general, the second wave was reported to
be bigger (Kawata et al., 2005).
The tsunami waves inundated the research areas to vari-ous extents in relation to tsunami size, offshore bathymetry and coastal zone topography (Szczuci´nski et al., 2006). The inundation distance varied from a few hundred meters to more than one kilometer inland (Fig. 1). For areas with averaged slope inclination of 1.5 to 3% (most common in the studied case), the inundation was partly correlated with slope inclination and runup height—generally shorter inun-dation distance and higher runup was in observed on steeper slopes (Szczuci´nski et al., 2006). The tsunami runup height at the maximum inundation limit usually varied from less than 3 m in the part of Kho Khao Island’s coast, which is protected by an offshore reef, to more than 6 m in north-ern and southnorth-ern Kho Khao Island and in Ban Bang Mor (Fig. 1(C)). Although the runup heights were partly con-trolled by topography, the areas of the highest runup (>6 m) coincided also with the sites where the highest wave height (∼tsunami flow depth) was reported. Tsuji et al. (2006) documented wave height to be over 12 m above sea level from the northern Kho Khao Island and over 15 m from its southern part and from the coast southward from the island (Ban Nham Kem). Tsunami wave height of more than 15 m was also reported from Pakarang Cape (Siripong, 2006). In the areas with smaller runup heights (<6 m) the wave heights measured close to the studied transects were up to 6.4 m (Tsuji et al., 2006). The tsunami wavefront wa-ter velocity, calculated from the videos of the tsunami, was estimated to reach 14.4 km h−1 in Phuket (Kawata et al., 2005) and 33± 4 km h−1 in Khao Lak (M˚ard Karlsson et
W. SZCZUCI ´NSKI et al.: 26 DECEMBER 2004 TSUNAMI DEPOSITS IN THAILAND 845
Fig. 1. The study area. (A) Coasts affected by IOT (bold line) and the location of the study area (in rectangle); (B) Part of the Andaman Sea coast of Thailand with marked surveyed areas. (C–D) Location of the studied sites, measured tsunami runup heights and inundation distances (after Szczuci´nski et al., 2006). Legend: (1) runup height [m], (2) inundated areas, (3) offshore contour lines, (4) inland water bodies, (5) earthquake epicenter and major rupture areas during the 2004 Sumatra-Andaman earthquake (after Subarya et al., 2006), (6) topographical transect lines presented in Figs. 3 and 4, (7) investigated trenches, (a) included in transects (Figs. 3 and 4); (b) remaining investigated sites, (8) forests, (9) roads, (10) sites shown in Fig. 2.
3.
Materials and Methods
The field study was carried out in January and February 2005, less than two months after the tsunami. At the time of the survey, the tsunami deposits were almost unaltered given that no rain was reported between the tsunami and the sampling. The investigations were preceded by a geode-tic survey with differential GPS (Leica SR530 GPS System 500) to document the inundated zone morphology and the tsunami runup. The runup is defined as the difference be-tween the elevations of the maximum tsunami penetration and the elevation of the shoreline at the time of the tsunami, which was corrected for the tidal phase difference between the time of the measurement and of the tsunami (Inter-governmental Oceanographic Commission, 2008). The de-tails for the applied correction procedure are documented in Szczuci´nski et al. (2006), and the tide gauge records from the time of the tsunami are from Tsuji et al. (2006). A handheld Garmin GPS was used to document the position of each sampling site.
The tsunami deposits were investigated in more than 80 pits (Fig. 1), usually located in the shoreline normal tran-sects. Apart from the beach zone sites, which are not in-cluded in this paper, the identification of the deposits was straightforward. At each site, the thickness of the tsunami deposit was measured. In the case of significant lateral thickness variations on a pit scale, an additional control pit was dug, and the thickness was measured within the pits at equally spaced distances to report an average value. The deposits were photographed and described, taking into ac-count the surface forms, the relation to the underlying hori-zon, the internal sedimentary structures and the major sed-iment components. In most of the investigated sites, bulk samples of the tsunami deposits were taken. In a majority of those pits in which significant vertical grain size change was clearly observed, each individual layer was sampled separately. Some samples of beach sediments and soils or sediments underlying the tsunami deposits were also taken. Additional observations, including notes on the tsunami de-posit extents and on the change in dede-posit thickness, were also made along the investigated transects.
All of the samples (N = 127) were subjected to a grain size analysis. The samples were dried and sieved into thirteen, 0.5 phi interval, grain-size fractions ranging from gravel to mud. If the mud fraction was>5%, the fraction smaller than sand (>4 phi) was further analysed with an optical diffractometry method on a laser diffraction-based Mastersizer 2000 Particle Analyzer. The data for the grain size<4 phi are represented as weight % (sieving results). The mud fraction obtained from the wet sieving was used as 100% for the optical diffractometry analysis. The data
>4 phi are represented as volume %. All of the results are
represented on a phi scale. The conversion of the metric scale into phi values is based on an equation:
phi() = − log2D
where D equals the size in mm. The grain size statistics (mean, sorting, skewness and kurtosis) were calculated us-ing the logarithmic method of moments with Gradistat soft-ware (Blott and Pye, 2001).
4.
Results
The characteristics of the tsunami deposits (Fig. 2) are presented in detail for twelve selected transect lines (see Fig. 1 for locations). They are presented in Figs. 3 to 6, which include data on topography, tsunami deposit thick-ness, sedimentary structures and grain size (mean, sorting, skewness, mud and gravel content). The data from sites separate from the transect lines are included in the datasets presented in Figs. 7 and 8 for the tsunami deposit thickness and grain size. The following subchapters summarise the sedimentary characteristics of the documented deposits.
To facilitate further discussion in the context of the vari-able impact of tsunami with various runup height, the stud-ied sites from the coast of Phang Nga province (transects 1 to 8), which are characterised by similar coastal environ-ments with analogous available sediment sources, were di-vided into two arbitrary, equally represented classes. The Phang Nga transects 2, 3, 4, and 8 are grouped into smaller runup class (<6 m), and transects 1, 5, 6, and 7 with runup
>6 m into the second class (Table 1). The topography and
sediment sources of transects from Phuket Island vary from the Phang Nga province coast, so they are not included in this discussion.
4.1 Tsunami deposit extent and thickness
Sedimentary deposits from the tsunami are found in most places where the tsunami flooding occurred and covered almost the entire inundation zone. Most deposits are in the form of continuous sand sheets or patches. Only in a very few places are boulders transported and left by the tsunami (e.g., Pakarang Cape). The tsunami deposits are usually missing in a belt 10 to 250 m wide next to the shoreline (Figs. 3 and 4) where erosion and/or sediment bypassing dominated. In some cases, no tsunami deposits are found close to the flooding limit. However, in places where the tsunami flooding was limited by a cliff or scarp, they tend to be relatively thick (e.g., transect 2 in Fig. 3).
The tsunami deposit thickness varies from millimeters (Fig. 2(C)) to more than 40 cm (Fig. 2(A)). However, in most of the trenches, it is less than 10 cm. The thicker accumulations of the deposits tend to be localised and are found mostly in depressions and on the seaward sides of small cliffs or scarps (Figs. 3 and 4). The deposits thicker than 30 cm are found only in a region approximately 100 to 150 m from the shoreline or just next to a beach. The thickness varies a lot on the transect scale (hundreds of me-ters). In some transects, the deposits are thicker with dis-tance from the shoreline, reaching a maximum value ap-proximately 100 m from the shoreline, and then they irreg-ularly become progressively thinner inland (e.g., transects 5 and 6 in Fig. 3; Fig. 7). Only in one case (transect 3, Fig. 3) is observed a continuous landward thinning trend. The lo-cal variability of the tsunami deposit thickness is related to the local topography (thinner over local elevations) and to obstacles (deposition on the leeward side of the obstacle) (Fig. 2(E), transect 2 in Fig. 3). An example of a lee side deposition is presented in Fig. 2(E), which shows a 10-m long ridge formed by unidirectional flow on the lee side of a tree; the site is close to the southern tip of Kho Khao Is-land, which was crossed by the tsunami (no backwash).
W. SZCZUCI ´NSKI et al.: 26 DECEMBER 2004 TSUNAMI DEPOSITS IN THAILAND 847
Fig. 2. Examples of IOT deposits. For locations see Fig. 1. (A) Example of 42-cm thick deposits with erosional basal contact. The deposits are composed of two units. The lower (28-cm thick) is densely laminated, moderately sorted coarse sand. The upper unit shows normally graded, poorly sorted sediments from coarse to very fine sand. (B) A 35-cm thick layer of tsunami deposits composed of very coarse sand with pieces of corals (up to 10 cm). The uppermost 10 cm consists of coarse sand. The deposits cover former soil with still preserved bent grass. (C) Example of a 2-cm thick tsunami deposit layer composed of poorly sorted medium sand conformably covering the former soil. (D) Example of 30-cm thick tsunami deposits with lower erosional contact, composed of approximately 15 cm of massive coarse sand covered with a layer of densely laminated medium sand. (E) Deposition on the lee side of an obstacle (tree). The 10-m long ridge behind the tree was primarily a result of scouring and succeeding deposition, producing two normally graded layers composed of coarse to very fine sand up to 15-cm thick. (F) Circular hollows in the tsunami deposits with small ripples inside indicating rotational flow. The hollows are in a row and were possibly created by a moving vortex. The first hollow is in a 16-cm thick tsunami deposit layer composed of well-sorted, massive fine sand. The lower contact is conformable. The white cover is due to salt crust. (G) Example of an 18-cm thick layer of moderately sorted, very fine sand with preserved current ripples at the surface (landward flow direction is marked with arrow).
tsunami runup height in comparable transects from Phang Nga coast (Fig. 7, Table 1). The thickest deposits are in transects with the highest runup. The averaged tsunami deposit layer thickness for a coast with a tsunami runup height less than 6 m is 8.5 cm (29 measurements), and for the sites with a runup greater than 6.0 m, 11.4 cm (34 measurements). The trends of tsunami deposits thickness also differ with regard to the runup height (Figs. 3 and 4, Table 1). In the case of the smaller runup transects,
the maximum thickness is usually closer to the shoreline, and then the deposits generally become thinner landward (transects 3 and 4 in Fig. 3, and transect 10 in Fig. 4). In some of the areas with the highest runups, the deposit thickness increase inland until it reached approximately 1/3 of the inundation distance, where the maximum is observed, and then the deposits thin landward (transects 1, 5 and 6 in Fig. 3). The fourth transect in this group (transect 7, Fig. 4) revealed three maxima, located at approximately 100, 450
Fig. 3. Topography and tsunami deposit properties along the investigated transects. See Fig. 1 for transect locations. For each transect, the following properties are presented: shore-perpendicular morphological profile up to the inundation limit (scales in [m]) with marked locations of trenches and simplified sedimentological logs of the investigated tsunami deposits (the size of the sedimentological logs is not to scale), T—thickness of tsunami deposits (scale in [cm]), M—mean grain size of tsunami deposits (scale in [phi]; if more than one sample was investigated in a profile, the samples are marked with letters; “a” stands for the uppermost sample), So—sorting (scale in [phi]), Sk—skewness (scale in [phi]), Mud—mud fraction content (scale in weight %) and Gr—gravel fraction content (scale in weight %). Legend for the simplified sedimentological logs: (1) very coarse sand, (2) coarse sand, (3) medium sand, (4) fine sand, (5) mud, (6) normal gradation, (7) erosional contact/sharp contact, (8) desiccation structures, (9) mud clasts, (10) coral reef fragments in sand matrix, (11) concrete blocks/plant fragments and coconut detritus and (12) samples taken only from a part of the tsunami deposits profile.
and 600 m landward, separated by areas covered by thinner deposits. The thickest deposits are found in a depression, and their deposition was probably enhanced by the local topography.
4.2 Tsunami deposit basal contacts
The tsunami deposits basal contacts are usually sharp or abrupt, making the identification of the IOT fairly simple (Fig. 2). The contacts are generally plain, though also fre-quently irregular or undulating, and are classified as either conformable (more than 70% of the studied sites) or
ero-sional (approximately 15% of the studied sites). In approx-imately 15% of the studied cases, it is not possible to iden-tify the type of contact with certainty. The conformable basal contacts are frequent when the deposits cover a previ-ously vegetated soil and bent plants are still preserved in the IOT deposits (Figs. 2(B, C, F)). The soil texture is usually distinct and dark. In some cases, artificial anthropogenic soil is found in the form of relocated lateritic material. In many cases, the soil is relatively hard (the IOT occurred during the dry season). The erosional contacts (Fig. 2(D))
W. SZCZUCI ´NSKI et al.: 26 DECEMBER 2004 TSUNAMI DEPOSITS IN THAILAND 849
Fig. 4. Topography and tsunami deposit properties along the investigated transects. See Fig. 1 for locations. For explanations, see Fig. 3.
are found mostly in the locations closest to the shoreline (within the first 100 m). Their evidence is highlighted by uprooted roots, rip up clasts and irregular contact surfaces.
4.3 Tsunami deposit relief
At most of the studied locations, the surface of the tsunami deposits is plain. However, in several places, there are preserved wave and current ripples (Fig. 2(G)), ridges on the lee side of obstacles (Fig. 2(E)) and rows of circu-lar hollows (Fig. 2(F)). Wave ripples of a small amplitude, up to 3 cm, are found at one site. Current ripple marks are much more common and are found near Nham Kem (Fig. 2(G)) and on the northern tip of Kho Khao Island. They are asymmetrical, have sinuous crests, lee side di-rected landward, wavelengths of 5 to 10 cm and heights usually less than 5 cm. A very peculiar form is found nearby in Bang Mor, where a line of circular hollows oc-curs (Fig. 2(F)). They were spaced at approximately 10- to 20-m intervals and decreased in size. The largest hollows are approximately 30 cm in diameter and are as deep as the
tsunami deposit layer (less than 20 cm). The hollows are in a massive tsunami deposits layer, and no erosion of the substrate is noted. The inner sides of the hollows are cov-ered with small ripples, suggesting a whirlpool-like water flow. The ripples and the circular hollows are documented only from the sites with a runup height of>6 m. In many places, the surfaces of the tsunami deposits are covered with mud cracks, organic debris (especially needles of Casuraina trees) (Fig. 2(A, C)) and salt crusts (Fig. 2(F)).
4.4 Tsunami deposit composition
The tsunami deposits are composed mainly of siliciclas-tic sand with an admixture of carbonates. In samples col-lected within 200 m of the shoreline, the sand fraction is composed of approximately 70% mostly subrounded min-eral grains (quartz, feldspars, heavy minmin-erals), approxi-mately 25% shell fragments and approxiapproxi-mately 5% ben-thic foraminifera tests. In a few areas close to the shore-line, the amount of shells and coral reef fragments is much greater. Occasionally, the deposits contain macrofauna
rem-Fig. 5. Example of vertical grain size changes in tsunami deposits. Site with two normally graded layers. See rem-Fig. 1 for location.
Fig. 6. Examples of lateral grain size changes in tsunami deposits in transects 4 and 5, which represent areas with low runup (2.9 m) and high runup (7.7 m), respectively.
nants (i.e., fish, turtles), grass, branches and various human artefacts (e.g., plastic). In a few cases, the IOT deposits contain the rip up clasts of older sediments. In a trench in transect 5 (Fig. 3), mud clasts more than 10 cm in diameter are found in a layer of almost 40 cm thick coarse sand. The mud clasts are of the same colour and composition as the underlying muddy sediments.
The detailed composition of a dozen or so of the samples presented here were already analysed and reported in
re-gards to microfossils (Kokoci´nski et al., 2009), heavy min-eral assemblages (Jagodzi´nski et al., 2009) and geochem-istry (Szczuci´nski et al., 2005; Kozak et al., 2008; Zioła-Frankowska et al., 2009).
4.5 Tsunami deposit internal structures
Internal layering is commonly observed in the tsunami deposits that are at least a few cm thick. The number of layers ranges from one to four. A single layer is the most common, and two layers exist in approximately 20% of the
W. SZCZUCI ´NSKI et al.: 26 DECEMBER 2004 TSUNAMI DEPOSITS IN THAILAND 851
Fig. 7. Tsunami deposits thickness for>6 m and <6 m tsunami runup classes along Phang Nga province transects with the outline of the thickest samples plotted against the distance from the shoreline. Note the thickness maxima of higher runup class to be more inland. Data from Phuket Island transects (all<6 m) are also included. The horizontal axis is logarithmic.
Fig. 8. Mean grain sizes of all the analysed tsunami deposits samples separated into two tsunami runup height classes plotted against the distance of the sampling points from the shoreline. The horizontal axis is logarithmic.
documented sites. Three layers are found in 3 trenches, and four layers are found at only one site. The multiple lay-ers are generally observed in deposits thicker than 15 cm; however, the thinnest tsunami deposits with two layers are only 4 cm thick. The layers are usually delineated with changes in the grain size and/or by the erosional contacts. Multiple layers are more common in transects with a runup
>6 m (Table 1). Regardless of the number of layers, certain
beds may be massive in structure (Fig. 2(C, F)), may reveal normal grading (fining upwards) (Fig. 5), reverse grading, plane parallel lamination (Fig. 2(A, B, D)), crossbedding (Fig. 2(D)), and scour and fill structures. Within a multi-layered tsunami deposit, particular layers may be of vari-ous kinds (Fig. 2(A)). The most common combination is a lower part composed of plane or cross laminated sands, reverse graded sands or of massive sediments and an upper
part composed of normally graded sediments.
A massive appearance is observed in approximately 45% of the investigated sites (Figs. 3 and 4). These deposits lack clear change in their grain size or macroscopically visible laminations. The massive structure is observed in deposits of various thickness, grain size (both in sand and muds) and distance from the shoreline. The massive layers are more common in areas with smaller runup (more than 50%) than in the regions with a higher runup (approximately 40%). A normal grading (fining upward) is the most common ap-pearance of the IOT layers. Along the Phang Nga coast it is found in almost 70% of the sites with a low runup height and in almost all of the sites with a higher runup (Table 1). A reverse grading is found only in 2 trenches located less than 200 m from the shoreline, forming the lowermost part of the tsunami deposits. Frequently, tsunami deposits are
Table 1. Comparison of selected IOT deposits characteristics from Phang Nga province transects of tsunami runup height<6 m and >6 m.
runup<6 m runup>6 m
transect No (Figs. 3 and 4) 2, 3, 4, 8 1, 5, 6, 7
No of samples analysed 27 64
for grain size
average thickness [cm] 8.5 11.4
maximum thickness [cm] 35 40
most common trend of one to three maxima: approximately maximum in approximately 1/3 landward tsunami deposits 100 m from shoreline and>150 m of the inundation distance or relatively
thickness changes from the shoreline uniform thick sediment blanket
throughout the inundation zone
average and maximum 1.5 (20.3) 2.8 (67.9)
(in brackets) % mud
average and maximum 28.7 (84.9) 11.8 (57.1)
(in brackets) % gravel
range and average value 0.6–5.6 (3.14) 0.02–5.8 (2.38)
(in brackets) of mean grain size [phi]
range and average value 0.7–1.99 (1.33) 0.46–3.11 (1.33)
(in brackets) of grain size sorting [phi]
range and average value −0.55–2.3 (1.0) −1.4–4.7 (0.81)
(in brackets) of grain size skewness [phi]
range and average value 2.5–16.6 (8.49) 1.4–60.9 (8.92)
(in brackets) of grain size kurtosis [phi]
% of sites with multiple 10% 41%
layers within tsunami deposits
% of sites with massive layers* 54 41
% of sites with normally 68 97
graded layers*
% of sites with laminated layers* 10 25
preserved surface no ripples and circular hollows
sedimentary bedforms
internal erosional contacts no in approximately 15% of sites
*at particular sites several layers of various types may occur; thus, the sum of massive, laminated and normally graded layers may be higher than 100%.
laminated. In the areas with higher runup more than 25% of the sites reveal a plane lamination. In the sites with lower runup and in the sites located more than 450 m from the coastline the plane lamination is less common. Cross lam-ination is less frequent and is found in a few sites close to the shoreline. The scour and fill structures recording two distinct depositional events are found in 5 trenches located within 200 m of the coastline in areas with a runup>6 m.
4.6 Tsunami deposit grain size distribution
The grain sizes of the tsunami deposits range from mud to boulders; however, the sand fraction dominates (Fig. 2). On average, the mud content is approximately 2% and rarely reaches more than 10%. The gravel fraction on average comprises 15% of the deposits, and in several samples, the gravel content is greater than 80%, with only a small sand admixture. Sometimes, larger pebbles and cobbles existed in the deposits (Fig. 2(B)). The boulders found at Pakarang Cape and elsewhere in the studied region are described in detail by Goto et al. (2007) and Yawsangratt et al. (2009) and are not described here.
The grain size distributions of the analysed samples
(Figs. 3–6 and 8, Table 1) revealed large variations. The mean grain size ranges from−0.61 phi (very coarse sand) to 5.78 phi (coarse silt). However, the mean for most of the samples was in medium, fine and very fine sand classes. The IOT deposits range from very poorly sorted to well sorted, but more than 50% of the analysed samples fall in the poorly sorted sediment class. Skewness describes the asymmetry of the grain size distribution. The tsunami de-posits represent the entire range of grain size distributions, from very coarse skewed to very fine skewed. Kurtosis de-fines the peakedness of the size distribution. The studied sediments also represent the entire range of grain size dis-tributions, from very platycurtic to very leptokurtic distribu-tions; the leptokurtic and very leptokurtic distribution types are the most common. From the four statistical parameters, only the mean and the sorting are slightly correlated (the correlation coefficient is 0.56). The finer sediments usually are more poorly sorted.
The vertical changes in the grain size are studied in 23 trenches (Figs. 3–5). The most common vertical change is normal grading, which is present in 19 trenches. The
W. SZCZUCI ´NSKI et al.: 26 DECEMBER 2004 TSUNAMI DEPOSITS IN THAILAND 853
tsunami deposits may consist of one normally graded layer, or they may consist of multiple layers, with one or two nor-mally graded layers (Fig. 5). In some of the IOT deposits, no clear vertical gradation was observed, or the gradation was inverse.
The landward trends in the sediment grain size are vari-able (Figs. 3, 4 and 6), although there is a very general fin-ing landward if the complete dataset is analysed (Fig. 8). The fining is not linear. It is visible if the maximum and minimum sizes are taken into account. The mean grain sizes in the coarse and medium sands dominate in the first 100 m from the shoreline. Further landward, the maximum mean grain size is in the medium and the fine sand classes. The mean grain sizes in the very fine sand and silt fractions are observed no closer than approximately 100 m to the shore-line.
The grain size distribution profiles are presented for tran-sects 4 (runup 2.9 m) and 5 (runup 7.7 m) in Fig. 6, which includes beach samples and some soil samples. In both tran-sects, general fining landward is visible. The beach samples and some of the soil samples present quite different grain size distributions from the tsunami deposits. This finding may suggest that most of the tsunami deposits come from other sources (e.g., seafloor erosion). However, the beach samples may not be representative, as they were sampled after the tsunami. In both transects (Fig. 6), the samples of the tsunami deposits collected closest to the shoreline sites (less than 100 m) are coarser and are similar to underly-ing soils. The more landward deposits are characterised by relatively similar distributions, although the variations were recorded particularly in trenches, where fining upward is common.
The IOT deposit grain sizes in the Phang Nga transects do not show a clear relation to the tsunami runup heights. The ranges of the observed values of the grain size statistics and their horizontal trends are similar for various runup values (Figs. 3 and 4, Table 1).
5.
Discussion
5.1 IOT deposits characteristics
The studied deposits reveal many characteristics typical for the recent tsunami deposits known from other case stud-ies (Table 2). For instance, the thickness of the tsunami deposits, in the range of a few mm to approximately 40 cm and being approximately 10 cm on average, is very simi-lar to those reported from the adjacent areas (Hori et al., 2007; Fujino et al., 2010), as well as from the other ar-eas affected by the IOT (e.g., Moore et al., 2006) or other tsunamis (e.g., Gelfenbaum and Jaffe, 2003). This study found common features such as normally graded and mas-sive layers. However, as a masmas-sive structure is observed on the basis of a macroscopic assessment in approximately 45% of the investigated sites, it appears that if investigated in detail through high resolution grain size analyses, sedi-ment peels or X-ray pictures, they could appear to be graded or laminated in many cases (Choowong et al., 2008a). The basal sharp contact is also a common feature, although in the studied cases, it is not often of erosional character, as reported from other studies (Peters and Jaffe, 2010).
Several characteristics represented in the studied deposits
were also found elsewhere, but they are not considered in common reviews as the most typical characteristics of tsunami deposits. For instance, parallel lamination was found relatively frequently, it already has been recorded in several previous studies of tsunami deposits (Srinivasalu et
al., 2007), however it is often considered to be a typical
fea-ture of storm deposits (Morton et al., 2007). Occasionally, layers with inverse grading have also been reported (Naruse
et al., 2010), and such layers were also found in this study.
There is also a group of features considered to be typical for tsunami deposits and being rare or absent in this study. For example, the common mud cups and rip-up clasts (Goff
et al., 2001; Gelfenbaum and Jaffe, 2003) require a certain
source of sediments (mud) as well as certain erosional con-ditions of cohesive soil or of mud substratum. In the present case, both are rare—sand is the dominant sediment source for the tsunami deposits, and the onshore erosion took place mostly on sandy soil, which does not favour production of rip-up clasts.
Some of the features associated with typical tsunami de-posits were not found in this study. One such feature is soft sediment deformation, which was reported in several tsunami deposits worldwide (Van Loon, 2009). The sedi-ment deformations were also found in the IOT deposits in Thailand in the form of truncated flame structures, but only in one unique setting (Matsumoto et al., 2008). Another feature not found in the studied IOT deposits is internal mud layering, which had been identified in the 1998 Papua New Guinea tsunami (Gelfenbaum and Jaffe, 2003).
The composition of the tsunami deposits is not a uni-versal feature because it largely depends on the available source sediments for transport. Thus, if well-sorted dune sand is the unique source sediment, then the tsunami de-posits will be of a similar type (Singarasubramanian et
al., 2006). However, if the source is composed of
vari-ous sediments, then the resulting deposits will be variable and poorly sorted. The most likely sediment sources in the present case are the beach and the shallow part of continen-tal shelf. The beach sands in the studied region are in the range of fine to very coarse sands, with the finest sediments present at the high tide level and the coarsest at the low tide level (Grzelak et al., 2009). The continental shelf down to 20 m is covered with mud (mostly silt), fine to very coarse sand and occasionally boulders (Di Geronimo et al., 2009; Feldens et al., 2009, 2012). Beach and the inner shelf ar-eas potentially offer all of the grain sizes observed in the onshore tsunami deposits and are variable enough to ex-plain the very poor sediment sorting. However, the beach samples collected shortly after the tsunami may not be a good representation of the pretsunami beach. Grzelak et al. (2009) compared beach samples taken from three beaches in Thailand: Tri Trang, Patong and a beach in northern Kho Khao Island. They compared the samples taken at the low tide line, mean sea level and high water line and at vari-ous time points—shortly after the tsunami (February 2005) and in subsequent Februaries (2006, 2007 and 2008). The beach sediments collected shortly after the tsunami were coarser, more poorly sorted and more negatively skewed than those in the following years, which likely represent the pre-tsunami conditions.
Table 2. Tsunami deposit identification criteria based on the compilation of recent tsunami deposits studies from Peters and Jaffe (2010) compared to the present case study.
characteristic recent tsunami deposits present case
(Peters and Jaffe, 2010)
basal contact most tsunami deposits have sharp sharp contact with underlying soil, contact with the underlying in some cases erosional
material, in many cases erosional
the deposit geometry most tsunami deposits forms sand sheet with sediment patches landward-thinning sand sheets, close to the shoreline and to the often patchy near the limit of inundation inundation limit; thickness usually
increases landward and then decreases; however, the trends are variable; for low runup heights, the thickness changes within the sand sheet may follow the landward thinning trend deposits thickness in range of 1–30 cm, the maximum vary from few mm to more than 40 cm
is 150 cm
number of depositional layers typically 1–4 layers, often the 1–4 layers, no correlation between number of layers decrease landwards the number of layers and distance
from shoreline
vertical grading normal grading is a common feature, normal grading is common, as are although ungraded deposits are ungraded (massive) deposits; in a also frequent; occasionally, few cases inverse grading is found inverse grading is present
mud cap thin layer of mud or finer material sometimes finer deposits at the top, often drape the top of deposits rare mud cup
rip-up clasts many deposits contain clasts of rare mud clasts and soil rip-up clasts material ripped up from the
underlying substrate (mud or soil)
boulders common, mainly coral boulders only in specific sites, coral and granite boulders, as well as blocks of concrete
sedimentary structures not common, truncated flame in approximately 15% of sites structures, cross bedding, parallel parallel laminations; moreover, laminations, scour and fill structures occasional cross bedding, scour
and fill structures
coastal sediment source tsunami deposits usually have a common benthic foraminifera, coastal source reflected in diatoms, shells, grain size similar composition, grain size, grain size to beach and nearshore sediments, texture, marine or coastal fossils; geochemical salinity indicators; some sediments may come from occasional plant fragments, human
terrestrial environments artefacts
Probably the most commonly reported characteristic of the tsunami deposits, which is not supported by the data in this study, is the landward thinning of the deposits (Dawson and Shi, 2000; Morton et al., 2007). The recent studies contain many examples of thickness trends in the tsunami deposits, which do not follow the landward thinning trend (Moore et al., 2006; Hori et al., 2007; Fujino et al., 2008; Goto et al., 2008). However, in most cases, the deviations from the trend were explained by the role of the local relief, plant cover, etc. (Hori et al., 2007). Because studies of the modern deposits often focus on one or a few transects, it is difficult to determine if a certain transect is an “exception” or represents the overall distribution of deposits. In the dataset of this study, the effect of the local morphology is evident (i.e., accumulations in front of scarps). However, from the analysis of various transects, it seems that most of them do not reveal typical tsunami deposit thickness trends,
even without major changes in the topography. In most of the sites, the maximum accumulation of the deposits is located approximately 100 to 300 m inland. Many of the tsunami deposit thickness transects reported in the literature also show the maximum deposition located some distance inland (Moore et al., 2006).
In the case of the commonly reported landward fining trend in tsunami deposits, a problem of the methodological approach appears. In many works, the bulk grain size of the tsunami deposits is analysed. Yet, several layers interpreted to be from various runups and even backwash phases are also reported. The bulk grain size analyses are an average of depositional effects from several different events, even as contrasting as uprush and backwash. In some places, many layers are preserved, and in others, just one is preserved; thus, it is likely that in some cases, the averaged record from several different events (e.g., runups, backwash) is
W. SZCZUCI ´NSKI et al.: 26 DECEMBER 2004 TSUNAMI DEPOSITS IN THAILAND 855
compared with a depositional record of just one event. If the coastal zone is the major source of the sediments, then the overall landward fining trend would be expected and is indeed observed in the present study, although some of the transects exhibit significant variability.
5.2 Tsunami deposits in areas of various runup heights
The studied transects from relatively similar coasts of Phang Nga province, allowed for the rough comparison of an impact of tsunami size on sedimentation. This study consideres the tsunami runup height as an indicator of the tsunami size, as in the available data on tsunami height (Tsuji et al., 2006) suggests that high runup was not only due to topographic effect. The available data demonstrates that the available sediment sources for the compared studied sites are similar.
The comparison of the IOT deposits in the areas of the two preselected classes of runup heights is shown in Table 1. Most of the considered characteristics reveal some differences between the groups. The first significant dif-ference is with regards to the quantity of the sediments deposited in various areas (as exemplified by the average IOT deposit thickness; thicker deposits exist in the areas of greater runup) and the way the deposits are distributed landward. In the case of the smallest runup, most of the deposits are left closer to the shoreline, and then the sandy layer generally decreases landward. With the higher runups, the accumulation is shifted landward. These finding may be explained by the bigger size of tsunami wave being capable of eroding more material over a larger area (both offshore and onshore) and of transporting more sediments, as well as losing the energy necessary to keep the sediments in trans-port further onshore. The limitation for the suggested rela-tionship is the amount of available source sediments for the erosion, such as with rocky coastlines.
If the proposed explanation is correct, then the sediment properties should also vary between the areas of various runup heights. In comparing the grain size statistics, such as mean or kurtosis, there is no difference between the various areas. However, the areas of greater runup appear to be enriched in the finest fraction. This trend is emphasised by much higher maximum values of mud content, sorting and skewness. An explanation for this could be provided by the observation of the offshore sediment distribution. Mud is locally common on the seafloor at a water depth greater than 5 m (Di Geronimo et al., 2009; Feldens et al., 2009, 2012). Larger quantities of mud in the onshore tsunami deposits on land may suggest that the seafloor erosion resulted from the bigger tsunami (as evidenced by a higher runup), is more efficient relative to a smaller tsunami (with smaller runup).
Additional differences in the IOT deposits in the areas of lower and higher tsunami runups include the domina-tion of normally graded layers and laminated layers and the presence of internal erosional contacts in the region with a higher runup. The more frequent normally graded sediments may be explained by deeper flooding from the tsunami. The deeper water depth offers the time necessary for the differential settling of various grain sizes. Larger velocities may cause the tsunami to erode not only the on-shore soils but also the sediments already deposited by the tsunami.
5.3 Insights into sedimentary processes during the IOT
Taking into account the large variability in the tsunami deposits and the complexity of the tsunami flooding, as ev-idenced by the available video footage and eyewitnesses records (Choowong et al., 2008b), the complete sedimen-tation history is unlikely to be reconstructed based on the evidence presented here. The accounts of the eyewitnesses vary with regards to the number of waves and the wave intensity (M˚ard Karlsson et al., 2009). Furthermore, the waves recorded as a single wave at the tidal gauges (Tsuji
et al., 2006) appeared at some portions of the coast to be a
series of at least two waves (M˚ard Karlsson et al., 2009). In many areas, the water ponded after the first flooding and did not withdraw until the end of the tsunami wave train (Choowong et al., 2008b). This makes it difficult and spec-ulative to connect particular sedimentary layers to a par-ticular tsunami wave or its phase (runup and backwash). The physical features preserved in the deposits directly rep-resent the physics of the sediment movement that existed at the final moments of the deposition, so it is not possi-ble to directly interpret the sediment transport mode (see Shanmugam (2012) for further discussion). Several authors suggested the presence of backwash deposits within mul-tilayered, normally graded tsunami deposits (Hori et al., 2007; Paris et al., 2007), but unless the interpretation is sup-ported by sedimentary structures formed during the back-flow (Choowong et al., 2008a), such an interpretation may be speculative as well. The backwash was concentrated in most of the IOT-affected regions as a kind of channelised flow (Umitsu et al., 2007; Fagherazzi and Du, 2008) and was more likely to erode than to deposit a new sedimentary layer.
The observed sedimentary deposits allowed to suggest that the sedimentation took place during several phases (in-undations), producing separate layers. Common presence of fining upward deposits suggests suspension settling to be dominating depositional process. The relatively com-mon massive layers may be the result of hyperconcentrated flow but also may be the result of the limited variability within the sediment grain size and of the short settling pe-riod, which is too short to permit grain size gradation. Re-verse gradation and planar lamination of some deposits im-ply also direct deposition from bed load. Moreover, many local features—for instance: lee side depositional ridges, rows of vortex-generated circular hollows, local rippled sur-faces, suggest complex tsunami flow pattern.
6.
Conclusion
This paper provides new, original data on the develop-ment of the tsunami deposits resulting from a large tsunami in areas of various tsunami runup heights. The deposits are characterised by a thickness as great as 40 cm, with vari-able locations of the areas of maximum accumulation (but often not next to the shoreline) and basal sharp contacts, frequent massive, normally graded or laminated layers and general landward fining of the tsunami deposit grain size. The comparison of the deposits with the typical features of tsunami deposits reveals that simple continuous landward thinning trend of the tsunami layer may not really exist.
The tsunami size (presented as the tsunami runup height) appears to be reflected in the resulting deposits for compa-rable parts of coastline. A larger tsunami forms thicker de-posits with the maximum accumulation located further in-land. These deposits are enriched with sediment grain size fractions more common in deeper waters (in this case, the mud fraction likely came from water deeper than 5 m), and because of the bigger flow depth, the normally graded lay-ers are more common.
Acknowledgments. The study was supported by Adam
Mick-iewicz University in Pozna´n, Poland and Department of Mineral Resources in Bangkok, Thailand. The authors appreciate to Mr. Somsak Potisat and to Mr. Apitchai Chvajarernpun—the Direc-tors General of the Department of Mineral Resurces of Kingdom of Thailand and the DMR’s Chief of Foreign Affairs, Dr. Sommai Techawan. We acknowledge also to all colleagues who helped us in lab or field work, in particular to Radosław Jagodzi´nski and Tinnakorn Tatong. We thank Shigehiro Fujino, an anonymous re-viewer and the editor Yuichi Nishimura, for constructive critical comments.
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